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祁连山新元古代中-晚期至早古生代火山作用与构造演化

夏林圻, 李向民, 余吉远, 王国强

夏林圻, 李向民, 余吉远, 王国强. 祁连山新元古代中-晚期至早古生代火山作用与构造演化[J]. 中国地质, 2016, 43(4): 1087-1138. DOI: 10.12029/gc20160401
引用本文: 夏林圻, 李向民, 余吉远, 王国强. 祁连山新元古代中-晚期至早古生代火山作用与构造演化[J]. 中国地质, 2016, 43(4): 1087-1138. DOI: 10.12029/gc20160401
XIA Lin-qi, LI Xiang-min, YU Ji-yuan, WANG Guo-qiang. Mid-Late Neoproterozoic to Early Paleozoic volcanism and tectonic evolution of the Qilian Mountain[J]. GEOLOGY IN CHINA, 2016, 43(4): 1087-1138. DOI: 10.12029/gc20160401
Citation: XIA Lin-qi, LI Xiang-min, YU Ji-yuan, WANG Guo-qiang. Mid-Late Neoproterozoic to Early Paleozoic volcanism and tectonic evolution of the Qilian Mountain[J]. GEOLOGY IN CHINA, 2016, 43(4): 1087-1138. DOI: 10.12029/gc20160401

祁连山新元古代中-晚期至早古生代火山作用与构造演化

基金项目: 

中国地质调查局综合研究项目 121201120133

中国地质调查局综合研究项目 12120115070601

中国地质调查局综合研究项目 12120101100015004

详细信息
    作者简介:

    夏林圻, 男, 1942年生, 博士, 研究员, 博士生导师, 主要研究方向:区域火山岩石学与地球动力学; E-mail:xlinqi@cgs.cn

  • 中图分类号: P511.3;P542.1

Mid-Late Neoproterozoic to Early Paleozoic volcanism and tectonic evolution of the Qilian Mountain

Funds: 

Supported by China Geological Survey Program 121201120133

Supported by China Geological Survey Program 12120115070601

Supported by China Geological Survey Program 12120101100015004

More Information
    Author Bio:

    XIA Lin-qi: XIA Lin-Qi, male, born in 1942, doctor, professor; senior researcher, supervisor of doctor candidates, engages in the study of regional volcanic petrology and geodynamics; E-mail:xlinqi@cgs.cn

  • 摘要:

    祁连山地区的新元古代中-晚期至早古生代火山作用显示系统地时、空变化,其乃是祁连山构造演化的火山响应。随着祁连山构造演化从Rodinia超大陆裂谷化-裂解,经早古生代大洋打开、扩张、洋壳俯冲和弧后伸展,直至洋盆闭合、弧-陆碰撞和陆-陆碰撞,火山作用也逐渐从裂谷和大陆溢流玄武质喷发,经大洋中脊型、岛弧和弧后盆地火山活动,转变为碰撞后裂谷式喷发。850~604 Ma的大陆裂谷和大陆溢流熔岩主要分布于祁连和柴达木陆块。从大约550 Ma至446 Ma,在北祁连和南祁连洋-沟-弧-盆系中广泛发育大洋中脊型、岛弧和弧后盆地型熔岩。与此同时,在祁连陆块中部,发育约522~442 Ma的陆内裂谷火山作用。早古生代洋盆于奥陶纪末(约446 Ma)闭合。随后,从约445 Ma至约428 Ma,于祁连陆块北缘发育碰撞后火山活动。此种时-空变异对形成祁连山的深部地球动力学过程提供了重要约束。该过程包括:(1)地幔柱或超级地幔柱上涌,导致Rodinia超大陆发生裂谷化、裂解、早古生代大洋打开、扩张、俯冲,并伴随岛弧形成;(2)俯冲的大洋板片回转,致使弧后伸展,进而形成弧后盆地;(3)洋盆闭合、板片断离,继而发生软流圈上涌,诱发碰撞后火山活动。晚志留世至早泥盆世(420~400 Ma),先期俯冲的地壳物质折返,发生强烈的造山活动。400 Ma后,山体垮塌、岩石圈伸展,相应发生碰撞后花岗质侵入活动。

    Abstract:

    Mid-Late Neoproterozoic to Early Paleozoic volcanism in the Qilian Mountain area, which shows systematic variations in space and time, seems to have been the volcanic response to the tectonic evolution of the Qilian Mountain. The volcanism gradually changed from rift-related and continental flood basaltic through MORB-type and island-arc and back-arc to post collisional rift-related eruptions along with the tectonic evolution of the Qilian Mountain shifting from rifting and break up of Rodinia through opening and spreading of the Early Paleozoic oceans, subduction of the oceanic slabs and back-arc extension and ocean closure to arc-continent and continent-continent collision. The continental rift-related and flood lavas with ages of 850-604 Ma are distributed mainly on the Qilian and Qaidam Blocks. The widespread MORB-type and "island-arc-backarc"-type lavas were generated from about 550 to 446 Ma in both the North Qilian and the South Qilian ocean-trench-arc-basin systems. In the meantime, the intracontinental rift related volcanism occurred in the central Qilian Block between about 522 and 442 Ma. The Early Paleozoic oceanic basins were closed at the end of Ordovician (about 446 Ma). Subsequent post-collisional volcanism occurred on the northern margin of the Qilian Block from about 445 to 428 Ma. Such spatial-temporal variations provide important constraints on the geodynamic processes that evolved at the depth to form the Qilian Mountain. These processes involved (1) upwelling of mantle plumes or a mantle superplume and subsequent rifting and break-up of Rodinia and subsequent opening, spreading and subduction of Early Paleozoic oceans followed by island-arc formation, (2) roll-back of the subducted oceanic slabs followed by back-arc extension and back-arc basin formation, (3) ocean closure and slab break-off followed by upwelling of asthenosphere and post-collisional volcanism. Intensive orogenic activities occurred in the Late Silurian and Early Devonian (about 420 to about 400 Ma) in response to the exhumation of the subducted crustal materials. Mountain collapse and lithosphere extension happened and formed post-collisional granitic intrusions at < 400 Ma.

  • 锗(Ge)是一种典型的稀散元素,其地壳丰度为1.5×10-6,主要富集在煤和铅锌矿床中。统计结果显示,闪锌矿是铅锌矿床中Ge的主要载体矿物,但不同类型铅锌矿床闪锌矿中Ge的含量存在差异。除热液脉型和浅成热液型铅锌矿床闪锌矿中Ge的含量较高(可达2500×10-6)外,其他主要类型(如喷流沉积型,SEDEX;火山块状硫化物型,VMS;密西西比河谷型,MVT,等)铅锌矿床闪锌矿中Ge的平均含量通常 < 300×10-6。本次发现贵州贵定竹林沟锌矿床闪锌矿中Ge的显著超常富集现象,现报道如下。

    在细致深入的矿床学和矿物学研究基础上,利用激光剥蚀等离子质谱仪(LA-ICP-MS)对竹林沟锌矿床主要金属矿物闪锌矿进行原位微量元素组成分析。统计闪锌矿中Ge等元素的富集特征,结合相关分析和以往研究成果,揭示竹林沟锌矿床中Ge的超常富集机制。

    竹林沟锌矿床闪锌矿中Ge的含量为592×10-6~1100×10-6(平均764×10-6表 1),锌矿石中Ge的平均品位97.9×10-6。闪锌矿LA-ICP-MS微区原位Ge含量分析资料显示,扬子板块及其周缘地区MVT铅锌矿床,如牛角塘、会泽、毛坪、富乐等,其闪锌矿中Ge的含量均 < 652×10-6,即便富乐矿床闪锌矿中Ge的含量最高,但其平均含量也仅为191×10-6,明显比竹林沟锌矿床闪锌矿中Ge的含量(特别是Ge的平均含量)低。

    表  1  竹林沟锌矿床闪锌矿部分元素含量(10-6)
    Table  1.  The part elemental contents of sphalerite from the Zhulingou Zn deposit(10-6)
    下载: 导出CSV 
    | 显示表格

    与世界上主要类型铅锌矿床闪锌矿LA-ICP-MS微区原位Ge含量分析资料相比,竹林沟矿床闪锌矿中Ge的含量比SEDEX(Ge含量通常 < 50×10-6)、VMS(Ge含量多数 < 100×10-6)和MVT(Ge含量n×10-6~n×102×10-6,Ge平均含量 < 300×10-6)等闪锌矿中Ge的含量高出一个数量级。竹林沟矿床闪锌矿中Ge的含量与法国Noailhac-Saint Salvy热液脉型Zn-Ge-Ag-Pb-Cd矿床(Ge平均含量750×10-6)和玻利维亚Porco浅成热液型Ag-Zn-Pb-Sn-Ge矿床(n×102×10-6~2500×10-6)等少数类型铅锌矿床闪锌矿中Ge的含量(特别是Ge的平均含量)相当。

    可见,竹林沟锌矿床闪锌矿中Ge的含量比目前已知扬子板块及其周缘地区MVT矿床闪锌矿中Ge的含量(特别是Ge的平均含量)都高,且明显高出全球主要类型(除岩浆热液型和热液脉型外)铅锌矿床闪锌矿中Ge的含量(特别是Ge的平均含量)一个数量级,具有显著超常富集特征(接近Ge地壳丰度的1000倍)。

    初步分析显示,竹林沟锌矿床闪锌矿中Zn与Ga和Cd之间具有正相关关系;相反,Fe与Ga和Cd之间均具有负相关关系,这表明该矿床闪锌矿中Ga和Cd很可能不是直接替代Zn而是替代Fe,与笔者前期认识基本一致。然而,不难发现该矿床闪锌矿中Zn与Ge之间呈一定的负相关关系,但Fe和Ge之间则呈一定的正相关关系,进一步地Zn与Fe之间具有显著的负相关关系,且Zn与Fe+Ge之间负相关性更显著(图 1)。目前,闪锌矿中主要有六种Ge替代Zn的方式:(1)2Cu++Cu2++Ge4+↔4Zn2+;(2)Ge2+↔Zn2+;(3)2Ag++Ge4+↔3Zn2+;(4)2Cu++Ge4+↔3Zn2+;(5)□(晶体空位)+Ge4+↔2Zn2+;(6)nCu+Ge↔(n+1)Zn。可见,这六种替代方式均不能解释竹林沟锌矿床闪锌矿Zn和Fe+Ge之间的强烈负相关关系。因此,笔者推测该矿床中Ge很可能是与Fe一起共同替代Zn进入闪锌矿晶格(Fe+Ge↔2Zn),是一种新的Ge替代方式。

    图  1  竹林沟锌矿床闪锌矿Zn-(Fe+Ge)相关图解
    Figure  1.  Relationship diagram of sphalerite Zn-(Fe+Ge)in the Zhulingou Zn deposit

    竹林沟锌矿床闪锌矿中显著超常富集锗,锗的富集程度接近1000倍,且锗与铁一起共同替代锌进入闪锌矿晶格,是一种新的锗替代方式。初步估算竹林沟锌矿床锗金属储量超过400 t,而竹林沟锌矿床外围还有半边街等锌矿床,初步预测研究区锗资源量可能达到超大型规模(>1000 t),一个新的国家级乃至世界级锗资源基地曙光已现。

    感谢科技部、国家自然科学基金委、云南省科技厅和云南大学对本项目的支持。

    致谢: 审稿专家对论文提出了宝贵修改意见, 在此致以诚挚的谢意!
  • 图  1   中国大地构造格架简图(示主要前寒武纪克拉通、陆块和显生宙造山带)

    Figure  1.   Tectonic framework of China illustrating the major Precambrian cratons and blocks and younger orogens

    图  2   祁连山地质略图(兼示主要火山岩带位置及其年龄)

    Figure  2.   Geological sketch map of the Qilian Mountain with localities of major volcanic rocks and their ages

    图  3   祁连山地质略图(兼示主要花岗岩体及其年龄)

    Figure  3.   Geological sketch map of the Qilian Mountain, showing major granitic plutons and their ages

    图  4   祁连山超高压变质岩和高压变质岩的同位素年龄

    Figure  4.   Isotopic ages of the ultrahigh pressure metamorphic rocks and high pressure metamorphic rocks in the Qilian Mountains

    图  5   a—祁连山地区祁连陆块中新元古界地层划分和对比; b—肃南县熬油沟朱龙关群剖面(据文献[116]修编)

    Ⅰ—龙关群下部岩系: 1—枕状辉石玄武岩; 2—含石英白云岩及白云岩; 3—枕状辉石玄武岩(有辉绿岩脉侵入); Ⅱ—朱龙关群中部岩系: 4—砂泥质板岩夹灰岩; 5—含砾(有火山岩砾)泥质板岩; 6—硅质板岩夹菱铁矿-赤铁矿层。Ⅲ―朱龙关群上部岩系: 7—含石英白云岩(有辉长岩脉侵入); 8—辉石玄武岩。Q—第四系; Ʃ—熬油沟蛇绿岩岩片(由被肢解的蛇纹岩、辉长岩、块状玄武岩和枕状玄武岩构成)

    Figure  5.   a-Stratigraphic division and correlation of Neoproterozoic strata in the Qilian Block from the Qilian Mountain; b-Geological section of the Zhulongguan Group from Aoyougou area of Sunan County (modified after reference [116])

    Ⅰ-The lower part of the Zhulongguan Group: 1-Pillow pyroxene-basalt; 2-Quartz-bearing dolomite and dolomite; 3-Pillow pyroxene-basalt into which diabase veins intruded.Ⅱ-The middle part of the Zhulongguan Group: 4-Sand-argillaceous slate with limestone; 5-Gravel-bearing argillaceous slate (with gravels of volcanic rock); 6-Siliceous slate with siderite-hematite bed.Ⅲ-The upper part of the Zhulongguan Group: 7-Quartz-bearing dolomite into which gabbro veins intruded; 8-Pyroxene-basalt. Q-Quaternary sediments; Ʃ-Aoyougou ophiolite slice (consisting of dismembered serpentinite, gabbro, and massive and pillow-like basalts)

    图  6   a—祁连陆块西北部朱龙关群玄武质熔岩, b—祁连陆块南部全吉群玄武质熔岩, c—祁连陆块东部兴隆山群玄武质熔岩和d—柴达木陆块北缘高压—超高压变质带中鱼卡榴辉岩(原岩与大陆溢流玄武岩相似)的Ti/Y–Nb/La分类图解(数据来源: (a): [19, 69, 116]; (b): [62]; (c): [63]; (d): [46, 51])

    Figure  6.   Classification of Mid-Late Neoproterozoic rift-related basaltic lavas of a-Zhulongguan Group in the northwestern Qilian Block, b-Quanji Group in the southern Qilian Block, c-Xinglongshan Group in the southeastern Qilian Block, and d-Yuka eclogites (protoliths similar to continental flood basalts) in the HPM-UHPM belt from northern margin of the Qaidam Block in terms of Ti/Y versus Nb/La (Data sources: (a): [19, 69, 116]; (b): [62]; (c): [63]; (d): [46, 51])

    图  7   祁连山新元古代中—晚期裂谷玄武质熔岩a, c, e—SiO2-Nb/Y图解(据[154])和b, d, f—FeOT/MgO-SiO2图解(据[155])

    图 7‒b, d, f分别适用于图 7‒a, c, e中的亚碱性火山岩;数据来源同图 6

    Figure  7.   a, c, e-SiO2 versus Nb/Y diagrams (after reference [154]) and b, d, f-FeOT/MgO versus SiO2 diagrams (after freference [155]) for Mid-Late Neoproterozoic rift-related basaltic lavas from the Qilian Mountain

    Fig. 7‒b, d, f show the sub-alkaline volcanic rocks as plotted in Fig. 7‒a, c, e respectively; Data sources as for Fig. 6

    图  8   a, b—祁连陆块西北部朱龙关群, c—祁连陆块南部全吉群, d—祁连陆块南部兴龙山群新元古代中晚期玄武质熔岩, e, f—柴达木陆块北缘高压-超高压变质带中鱼卡榴辉岩(原岩与大陆溢流玄武岩相似)的不相容微量元素原始地幔(据[156])标准化蛛网图; g—朱龙关群、全吉群、兴龙山群新元古代中晚期裂谷玄武质熔岩和鱼卡榴辉岩(原岩与大陆溢流玄武岩相似)的La/ Ba-La/Nb图解; h—朱龙关群新元古代中晚期裂谷玄武质熔岩和鱼卡榴辉岩(原岩与大陆溢流玄武岩相似)的Nb/La-ɛNd(t)图解

    图 8-a~f中, 洋岛玄武岩(OIB)据[156]; 图中阴影区表示消减带玄武岩的成分范围, 其上限和下限分别由高-K玄武岩和低-K玄武岩的平均值(据[157])限定; 图 8-g中, 岩石圈混染效应导致成分点向高La/Nb和低La/Ba方向迁移; 洋岛玄武岩(OIB)的成分范围据[158, 159]数据来源同图 6

    Figure  8.   Primitive mantle (after reference [156]) normalized incompatible trace-element spider diagrams for Mid-Late Neoproterozoic basaltic lavas of a, b-Zhulongguan Group in the northwestern Qilian Block, c-Quanji Group in the southern Qilian Block, d-Xinglongshan Group in the southeastern Qilian Block, and e, f-Yuka eclogites (protoliths similar to continental flood basalts) in the HPM-UHPM belt from northern margin of the Qaidam Block; g-La/Ba versus La/Nb plots for Mid-Late Neoproterozoic rift-related basaltic lavas of Zhulongguan Group, Quanji Group, Xinglongshan Group and Yuka eclogites (protoliths similar to continental flood basalts); h-Nb/La versus ɛNd(t) diagram for Mid-Late Neoproterozoic rift-related basaltic lavas of Zhulongguan Group and Yuka eclogites (protoliths similar to continental flood basalts)

    In Fig. 8-a-f, patterns for oceanic island basalts (OIB) are from [156]. The shaded area shows the range for subduction-zone basalts, with the lower and upper limits being defined by"average"low-K and high-K basalts, respectively (after [157]). In Fig. 8-g, the dispersion to higher La/ Nb and lower La/Ba may represent the effects of lithospheric contamination. Field for oceanic island basalts (OIB) after reference [158, 159]; data sources as for Fig. 6

    图  9   祁连山新元古代中—晚期裂谷玄武质熔岩形成的构造环境判别图解a—Zr/Y-Zr图解(据[160]); b—Th/Yb-Ta/Yb图解(据[161]); c—Hf/3‒Th‒Ta图解(据[162]); d—Hf/3‒Th‒Nb/16图解(据[162]); e—祁连山新元古代中-晚期裂谷玄武质熔岩的Zr/Y-Nb/Y图解(据[167])

    缩写符: UC—上部陆壳; CB—受到大陆壳或/和大陆岩石圈混染的大陆玄武岩; PM—原始地幔; DM—浅部亏损地幔; HIMU—高-µ(U/Pb)源; EM1和EM2富集地幔源; OIB—洋岛玄武岩; DEP—深部亏损地幔; EN—富集组分; REC—再循环组分数据来源同图 6

    Figure  9.   Tectonic setting of Mid-Late Neoproterozoic rift-related basaltic lavas from the Qilian Mountain a-Zr/Y versus Zr diagram (after [160]); b-Th/Yb versus Ta/Yb diagram (after [161]); c-Hf/3‒Th‒Ta diagram (after [162]); d-Hf/3‒Th‒Nb/16 diagram (after reference [162]); e-Zr/Y versus Nb/Y diagram (after reference [167]) for Mid-Late Neoproterozoic riftrelated basaltic lavas from the Qilian Mountain

    Abbreviations: UC-Upper continental crust; CB-Contaminated (by continental crust or/and subcontinental lithosphere) basalts; PM-Primitive mantle; DM-Shallow depleted mantle; HIMU-High-µ(U/Pb) source; EM1 and EM2-Enriched mantle sources; OIB-Oceanic island basalt; DEP-Deep depleted mantle; EN-Enriched component; REC-Recycled component Data sources as for Fig. 6

    图  10   大约750 Ma前Rodinia超大陆裂解状态复原图(据[177]修编)

    Figure  10.   Cartoon diagram showing the breakup of Rodinia at. ca. 750 Ma (modified after reference [177])

    图  11   北祁连山仰冲的新元古代晚期—寒武纪洋壳(蛇绿岩)残片中玄武岩的a—SiO2-Nb/Y图解(据[154])和b—FeOT/MgO-SiO2图解(据[155])

    图 11-b适用于图 11-a中的亚碱性火山岩;数据来源: [14, 16-18, 66, 67, 69, 70, 81]

    Figure  11.   a−SiO2 versus Nb/Y diagrams (after reference [154]) and b−FeOT/MgO versus SiO2 diagrams (after reference [155]) for basalts in the obducted slices of Late Neoproterozoic−Cambrian ocean−crust (ophiolites) from the North Qilian Mountain

    Fig. 11-b shows the sub−alkaline volcanic rocks as plotted in Fig. 11-a; Data sources: [14, 16-18, 66, 67, 69, 70, 81]

    图  12   北祁连山仰冲的新元古代晚期—寒武纪洋壳(蛇绿岩)残片中玄武岩的不相容微量元素原始地幔(据[156])标准化蛛网图

    洋岛玄武岩(OIB)、E型洋脊玄武岩(E−MORB)和N型洋脊玄武岩(N−MORB)据[156]数据来源同图 11

    Figure  12.   Primitive mantle (after reference [156]) normalized incompatible trace−element spider diagrams for basalts in the obducted slices of Late Neoproterozoic−Cambrian ocean−crust (ophiolites) from the North Qilian Mountain

    Patterns for oceanic island basalts (OIB), E−type mid−ocean ridge basalts (E−MORB) and N−type mid−ocean ridge basalts (N−MORB) after reference [156] Data sources as for Fig. 11

    图  13   北祁连山仰冲的新元古代晚期—寒武纪洋壳(蛇绿岩)残片中玄武岩的构造环境判别图解

    a—2Nb−Zr/4−Y图解(据[183]); b—Ti/100‒Zr‒3Y图解(据[184]); c—Zr/Y-Zr图解(据[160]); d—玉石沟蛇绿岩中玄武岩的εNd(t)-87Sr/86Sr(t)图解(据[185]) UC—上地壳; LC—下地壳; EMⅠ和EMⅡ—富集地幔源Ⅰ和Ⅱ; HIMU—高μ地幔源; DM—亏损地幔源数据来源同图 11

    Figure  13.   Tectonic setting of basalts in the obducted slices of Late Neoproterozoic−Cambrian ocean−crust (ophiolites) from the North Qilian Mountain

    a−2Nb−Zr/4−Y diagram (after reference [183]); b−Ti/100−Zr−3Y diagram (after reference [184]); c−Zr/Y vesus Zr diagram (after reference [160]); d−εNd(t) versus 87Sr/86Sr(t) diagram for the basalts in the Yushigou ophiolite (after reference [185]) UC-Upper crust; LC−Lower crust; EMⅠand EMⅡ-Enriched mantleⅠandⅡsources; HIMU-High−µmantle source; DM−Depleted mantle source Data sources as for Fig. 11

    图  14   北祁连山中寒武世—奥陶纪弧火山岩的a, c, e, g—SiO2-Nb/Y图解(据[154])和b, d, f, h—K2O-SiO2图解(据[190])数据来源: (a, b): [13, 14, 16, 17, 20]; (c, d): [14, 16, 17, 72]; (e, f); [19, 20, 191]; (g, h): [76]

    Figure  14.   a, c, e, g−SiO2 versus Nb/Y diagrams (after reference [154]) and b, d, f, h−K2O versus SiO2 diagrams (after reference [190]) for Middle Cambrian-Ordovician arc−related volcanic rocks from the North Qilian Mountain Data sources: (a, b): [13, 14, 16, 17, 20]; (c, d): [14, 16, 17, 72]; (e, f): [19, 20, 191; (g, h): [76]

    图  15   北祁连山中寒武世—奥陶纪弧火山岩的a, c, e, g—不相容微量元素原始地幔(据[156])标准化蛛网图和b, d, f, h—Th/Yb-Ta/Yb图解(据[161])

    图中阴影区表示弧亚碱性玄武岩的成分范围, 其下限和上限分别由低‒K玄武岩和高‒K玄武岩的平均值(据[157])限定数据来源同图 14

    Figure  15.   a, c, e, g−Primitive mantle (after reference [156]) normalized incompatible trace−element spider diagrams and b, d, f, h−Th/ Yb versus Ta/Yb diagrams (after reference [161]) for Middle Cambrian−Ordovician arc−related volcanic rocks from the North Qilian Mountain

    The shaded area shows the range for arc sub−alkaline basalts, with the lower and upper limits being defined by"average"low−K and high−K basalts, respectively (after reference [157]) Data sources as for Fig. 14

    图  16   a, b—北祁连山中寒武世—奥陶纪弧火山岩的εNd(t)-87Sr/86Sr(t)图解(据[185])

    UC—上地壳; LC—下地壳; EMⅠ和EMⅡ—富集地幔源Ⅰ和Ⅱ; HIMU—高μ地幔源; DM—亏损地幔源数据来源同图 14

    Figure  16.   a, b−Plots ofεNd(t) versus 87Sr/86Sr(t) for Middle Cambrian−Ordovician arc−related volcanic rocks from the North Qilian Mountain (diagram after [185])

    UC-Upper crust; LC−Lower crust; EMⅠand EMⅡ-Enriched mantleⅠandⅡsources; HIMU-High−μmantle source; DM−Depleted mantle source Data sources as for Fig. 14

    图  17   北祁连山边马沟—肃南地区早古生代岛弧和弧后盆地地质略图(据[20]修编)

    Figure  17.   Geological sketch map of the early Paleozoic island arc and back−arc basins in the Bianmagou-Sunan area of the North Qilian Mountain (modified after reference [20])

    图  18   a, b—北祁连山大坂—大岔地区火山岩(517~469 Ma)和c, d—柴北缘滩涧山群火山岩(514~486 Ma)的SiO2-Nb/Y图解(图解据[154])和FeOT/MgO-SiO2图解(图解据[155])

    图b, d分别适用于图a, c中的亚碱性火山岩; 数据来源: (a, b): [16-19, 78, 79, 192]; (c, d): [57, 58]

    Figure  18.   SiO2 versus Nb/Y diagrams (after reference [154]) and FeOT/MgO versus SiO2 diagrams (after reference [155]) for a, b−Volcanic rocks (517-469 Ma) in the Daban−Dacha area of the North Qilian Mountain and c, d−Tanjianshan Group volcanic rocks (514-486 Ma) from the North Qaidam

    Fig. 18−b, d show the sub−alkaline volcanic rocks as plotted in Fig 18−a, c; Data sources: (a, b): [16-19, 78, 79, 192]; (c, d): [57, 58]

    图  19   北祁连山大坂—大岔地区火山岩(517~469 Ma)和柴北缘滩涧山群火山岩(514~486 Ma)的a, c—不相容微量元素原始地幔(据[156])标准化蛛网图和b, d—3Tb-Th-2Ta图解(据[193])

    洋岛玄武岩(OIB)、E型洋脊玄武岩(E-MORB)和N型洋脊玄武岩(N-MORB)据[156]; 弧后拉斑玄武岩(BAT)据[194]数据来源同图 18

    Figure  19.   a, c-Primitive mantle (after reference [156]) normalized incompatible trace-element spider diagrams and b, d-3Tb-Th-2Ta diagrams (after reference [193]) for the volcanic rocks (517~469 Ma) in the Daban-Dacha area of the North Qilian Mountain and the Tanjianshan Group volcanic rocks (514~486 Ma) from the North Qaidam

    Patterns for oceanic island basalts (OIB), E-type mid-ocean ridge basalts (E-MORB) and N-type mid-ocean ridge basalts (N-MORB) after reference [156]. Patterns for back-arc tholeiites (BAT) after reference [194] Data sources as for Fig. 18

    图  20   北祁连山弧后盆地火山岩(490~449 Ma)的a, c, e—SiO2-Nb/Y图解(图解据[154])和b, d, f—FeOT/MgO-SiO2图解(图解据[155])

    图b, d, f分别适用于图a, c, e中的亚碱性火山岩; 数据来源: (a, b): [16-20, 77, 191]; (c, d): [16-20, 195]; (e, f): [16-18]

    Figure  20.   a, c, e-SiO2 versus Nb/Y diagrams (after Winchester and Floyd, 1977) and b, d, f-FeOT/MgO versus SiO2 diagrams (after Miyashiro, 1975) for the volcanic rocks (490-449 Ma) in the back-arc basins from the North Qilian Mountain

    b, d, f show the sub-alkaline volcanic rocks as plotted in Fig. 20 a, c, e Data sources: (a, b): [16-20, 77, 191]; (c, d): [16-20, 195]; (e, f): [16-18]

    图  21   北祁连山弧后盆地玄武质熔岩(490~449 Ma)的a, c, e—不相容微量元素原始地幔(据[156])标准化蛛网图和b, d, f—3Tb−Th−2Ta图解(据[193])

    洋岛玄武岩(OIB)、E型洋脊玄武岩(E−MORB)和N型洋脊玄武岩(N−MORB)据[156]; 弧后拉斑玄武岩(BAT)据[194]数据来源同图 20

    Figure  21.   a, c, e−Primitive mantle (after reference [156]) normalized incompatible trace−element spider diagrams and b, d, f−3Tb−Th−2Ta diagrams (after reference [193]) for the basaltic lavas (490−449 Ma) in the Back−arc basins from the North Qilian Mountain

    Patterns for oceanic island basalts (OIB), E−type mid−ocean ridge basalts (E−MORB) and N−type mid−ocean ridge basalts (N−MORB) after reference [156]. Patterns for back−arc tholeiites (BAT) after reference [194] Data sources as for Fig. 20

    图  22   北祁连山大坂—大岔地区玻安岩的a—MgO-SiO2图解, b—TiO2−SiO2图解, c—Ni−Cr图解和d—REE球粒陨石(据[201])标准化蛛网图; e和f—老虎山和九个泉—卡马尔沟弧后盆地中玄武岩的εNd(t)-87Sr/86Sr(t)图解, 图解据[185]

    北祁连山大坂—大岔地区玻安岩的a—MgO-SiO2图解, b—TiO2−SiO2图解, c—Ni−Cr图解和d—REE球粒陨石(据[201])标准化蛛网图; e和f—老虎山和九个泉—卡马尔沟弧后盆地中玄武岩的εNd(t)-87Sr/86Sr(t)图解, 图解据[185]

    Figure  22.   a−MgO versus SiO2 diagram, b−TiO2 versus SiO2 diagram, c−Ni versus Cr diagram and d−Chondrite (after reference [201]) normalized spider diagram for the boninites in the Daban−Dacha area from the North Qilian Mountain; e and f−Plots ofεNd(t) versus 87Sr/86Sr(t) for the basalts in the Laohushan and the Jiugequan−Kamargou back−arc basins (diagrams after [185])

    UC-Upper crust; LC−Lower crust; EMⅠand EMⅡ-Enriched mantleⅠandⅡsources; HIMU-High−µmantle source; DM−Depleted mantle source Data sources as for Fig. 18 and Fig. 20

    图  23   北祁连山弧后盆地构造演化示意图(显示地幔对流方式和熔体产生过程的变化, 据[20]修编)

    A—早期的岛弧裂谷化没有扰乱地幔中岛弧岩浆生成的正常过程, 悬浮的底辟体克服周围地幔由于消减板片俯冲引起的下沉而上升, 产生岛弧熔体, 这些熔体从岛弧转向附近的裂谷区; B—弧后海底扩张体制的建立反映弧后盆地扩张脊之下地幔的上隆, 从而导致近于绝热状态的柱状地幔发生减压熔融, 这一过程和正常洋中脊处发生的作用相似。随着底辟体克服周围下沉的地幔流上升, 继续产生岛弧岩浆, 但是, 此时弧后拉伸轴已与岛弧火山前峰分离, 从而发育正常岩浆弧

    Figure  23.   Schematic representation of tectonics showing changing patterns of mantle convection and processes of melt generation associated with the evolving back-arc basin now preserved in the North Qilian Mountain (modified after reference [20])

    A-Early island-arc rifting did not disturb normal processes of arc magmagenesis in the mantle. Arc melts resulted from the rise of buoyant diapirs at a rate that allowed these to overcome the ambient mantle down flow induced by the subducting slab. These melts were diverted from the arc to the nearby rift axis; B-Establishment of a seafloor-spreading regime reflects establishment of a zone of mantle upwelling beneath the spreading ridge in the back-arc basin, resulting in decompression melting of a nearly adiabatic mantle column indistinguishable from that of normal mid-ocean ridges. Arc magmas continued to be generated and to diapirically ascend against ambient downward mantle flow, but the separation of the extension axis and the arc volcanic front allowed development of a normal magmatic arc

    图  24   祁连陆块拉脊山地区寒武纪—奥陶纪火山岩的a—SiO2-Nb/Y图解(图解据[154])和b—FeOT/MgO-SiO2图解(图解据[155]); 祁连陆块拉脊山地区寒武纪-奥陶纪玄武质熔岩的c—Nb/La-Ti/Y图解和d—La/Ba-La/Nb图解

    图 24‒b适用于图 24‒a中的亚碱性火山岩数据来源: [14, 206]

    Figure  24.   a-SiO2 versus Nb/Y diagram (after reference [154]) and b-FeOT/MgO versus SiO2 diagram (after reference [155]) for Cambrian to Ordovician volcanic rocks in the Lajishan area of the Qilian Block; c-Nb/La versus Ti/Y diagram and d-La/Ba versus La/Nb diagram for Cambrian to Ordovician basaltic lavas in the Lajishan area of the Qilian Block

    Fig. 24 b shows the sub-alkaline volcanic rocks as plotted in Fig. 24-a Data sources: references [14, 206]

    图  25   a, b—连陆块拉脊山地区寒武纪—奥陶纪玄武质熔岩的不相容微量元素原始地幔(据[156])标准化蛛网图; 祁连陆块拉脊山地区寒武纪—奥陶纪裂谷玄武质熔岩形成的构造环境判别图解: c—Zr/Y-Zr diagram (图解据[160]); d—Ce/Yb-Ta/ Yb图解(图解据[161]); e—3Tb‒Th‒2Ta图解(图解据[193])

    图 25-a, b中, 洋岛玄武岩(OIB)据[156]; 图中阴影区表示消减带玄武岩的成分范围, 其上限和下限分别由高-K玄武岩和低-K玄武岩的平均值(据[157])限定数据来源同图 24

    Figure  25.   a, b-Primitive mantle (after reference [156]) normalized incompatible trace-element spider diagrams for Cambrian to Ordovician basaltic lavas in the Lajishan area of the Qilian Block. Tectonic setting of Cambrian to Ordovician rift-related basaltic lavas in the Lajishan area of the Qilian Block. c-Zr/Y versus Zr diagram (after reference [160]); d-Ce/Yb versus Ta/Yb diagram (after reference [161]); e-3Tb‒Th‒2Ta diagram (after reference [193])

    In Fig. 25-a, b, the patterns for oceanic island basalts (OIB) are after reference [156]; the shaded area shows the range for subduction-zone basalts, with the lower and upper limits being defined by"average"low-K and high-K basalts, respectively (after reference [193]) Data sources as for Fig. 24

    图  26   祁连陆块北缘晚奥陶世—早志留世(445~428 Ma)火山岩的a—SiO2-Nb/Y图解(图解据[154])和b—FeOT/MgO-SiO2图解(图解据[155]); 祁连陆块北缘晚奥陶世—早志留世(445~428 Ma)玄武质熔岩的c—Nb/La-Ti/Y图解, d—La/Ba-La/Nb图解, 和e, f—不相容微量元素原始地幔(据[156])标准化蛛网图

    图 26‒b适用于图 26‒a中的亚碱性火山岩; 图 26‒d中, 岩石圈混染效应导致成分点向高La/Nb和低La/Ba方向迁移; 洋岛玄武岩(OIB)的成分范围据[158, 159]; 图 26‒e, f中, 洋岛玄武岩(OIB)据Sun & McDonough (1989);图中阴影区表示消减带玄武岩的成分范围, 其上限和下限分别由高-K玄武岩和低-K玄武岩的平均值(据[157])限定数据来源: [16, 17]

    Figure  26.   a-SiO2 versus Nb/Y diagram (after reference [154]) and b-FeOT/MgO versus SiO2 diagram (after reference [155]) for Late Ordovician-Early Silurian (445-428 Ma) volcanic rocks on the northern margin of the Qilian Block; c-Nb/La versus Ti/Y diagram, (d-La/Ba versus La/Nb diagram; and e, f-Primitive mantle (after [156]) normalized incompatible trace-element spider diagrams for Late Ordovician-Early Silurian (445-428 Ma) basaltic lavas on the northern margin of the Qilian Block

    Fig. 26-b shows the sub-alkaline volcanic rocks as plotted in Fig. 26-a. In Fig. 26-d, the dispersion to higher La/Nb and lower La/Ba ratios may represent the effects of lithospheric contamination. Field for oceanic island basalts (OIB) is after references [158, 159]. Patterns for oceanic island basalts (OIB) are from reference [156]. In Fig. 26-e, f, the shaded area shows the range for subduction-zone basalts, with the lower and upper limits being defined by"average"low-K and high-K basalts, respectively (after reference [157]) Data sources: references [16, 17]

    图  27   祁连陆块北缘晚奥陶世—早志留世(445~428 Ma)玄武质熔岩形成的构造环境判别图解

    a—Zr/Y-Zr图解(据[160]); b—Th/Yb-Ta/Yb图解(据[161]); c—Hf/3‒Th‒Ta图解(据[162]); d—Hf/3‒Th‒Nb/16图解(据[162]); e—祁连陆块北缘晚奥陶世—早志留世(445~428 Ma)玄武质熔岩的Nb/La-εNd(t)图解数据来源同图 26

    Figure  27.   Tectonic setting of Late Ordovician-Early Silurian (445-428 Ma) basaltic lavas on the northern margin of the Qilian Block

    a-Zr/Y versus Zr diagram (after reference [160]); b-Th/Yb versus Ta/Yb diagram (after reference [161]); c-Hf/3‒Th‒Ta diagram (after reference [162]); d-Hf/3‒Th‒Nb/16 diagram (after reference [162]); e-Nb/La versus εNd(t) diagram for Late Ordovician-Early Silurian (445-428 Ma) basaltic lavas on the northern margin of the Qilian Block Data sources as for Fig. 26

    图  28   祁连山新元古代—古生代构造岩浆演化阶段示意图

    A—新元古代, Rodinia超大陆裂解导致全球性早古生代大洋(包括北祁连洋和南祁连洋)打开;B—早古生代大洋岩石圈以低角度向北俯冲-消减, 导致弧火山作用;C—大约自早寒武世(约520 Ma)起, 北祁连和南祁连大洋板片回转, 相伴发生软流圈上涌, 导致弧后岩石圈伸展和弧后盆地火山作用;与此同时(525~442 Ma), 包括拉脊山和化隆地区在内的祁连陆块的中部, 则是处于陆内裂谷环境;D—北祁连洋和南祁连洋的最终闭合分别发生于445 Ma和441 Ma;大约在445 Ma, 北祁连大洋板片断离, 诱使软流圈上涌, 导致在祁连陆块北缘发生445~428 Ma的碰撞后裂谷火山活动;大约自440 Ma始, 柴达木大陆岩石圈开始深俯冲;E—大约自423 Ma始, 俯冲的北祁连洋壳开始折返;大约在420~400 Ma, 南祁连板片断离, 致使俯冲的南祁连板片折返, 形成柴北缘高压-超高压变质带;F—晚泥盆世, 祁连造山系开始垮塌;在大约400~370 Ma期间, 连续的岩石圈伸展和拆沉, 致使发生地壳熔融和强烈的岩浆活动, 形成许多碰撞后花岗质侵入体

    Figure  28.   Sketch map showing the stages of Qilian Mountain Neoproterozoic-Paleozoic tectonomagmatic evolution

    A-The global Early Paleozoic Ocean, including the North Qilian Ocean and the South Qilian Ocean, was opened in the Neoproterozoic as the consequence of breakup of supercontinent Rodinia. B-Carton, showing the north-dipping, low-angle subduction of the Early Paleozoic oceanic lithosphere, which resulted in the arc volcanism. C-Carton: illustrating the back-arc lithospheric extension and back-arc basin volcanism in both North Qilian and South Qilian back-arc basins that occurred as a result of upwelling of asthenosphere accompanied by roll-back of the North Qilian and South Qilian oceanic slabs since early Cambrian (about 520 Ma). In the meantime (525-442 Ma), the central part of the Qilian Block, including the Lajishan and the Hualong areas, was in an intracontinental rift-related setting. D-The final closure of the North Qilian Ocean and the South Qilian Ocean took place at 445 Ma and 441 Ma, respectively. The break-off of the North Qilian oceanic slab at about 445 Ma induced an upwelling of asthenosphere, which gave rise to the 445-428 Ma post-collisional rift-related volcanism on the north margin of the Qilian Block. At about 440 Ma, the Qaidam continental deep subduction started. E-At about 423 Ma, the subduced North Qilian oceanic crust started to exhume. The subducted South Qilian slab started to exhume, forming the North Qaidam HPM-UHPM belt, as a result of South Qilian slab break off at 420-400 Ma. F-In the late Devonian, the Qilian orogenic system started to collapse; continuous lithosphere extension and delamination resulted in crust melting and strong magmatic activity and formed a number of post-collisional granitic intrusions with the ages of 400-370 Ma

    表  1   祁连山新元古代—早古生代火山岩、蛇绿岩和超镁铁质岩的年龄数据

    Table  1   Compiled age data of Neoproterozoic-Early Paleozoic volcanic rocks, ophiolites and ultramafic rocks in the Qilian Mountain

    下载: 导出CSV

    表  2   北祁连山高压变质带中高压变质岩石的年龄数据

    Table  2   Compiled age data of HPM rocks in the HPM belt from the North Qilian Mountains

    下载: 导出CSV

    表  3   祁连山古生代花岗岩类年龄数据

    Table  3   Compiled age data on Paleozoic granites in the Qilian Mountain

    下载: 导出CSV

    表  4   柴北缘高压、超高压变质带中高压、超高压变质岩石的年龄数据

    Table  4   Compiled age data on HPM−UHPM rocks of the Northern Qaidam HPM−UHPM belt

    下载: 导出CSV
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  • 收稿日期:  2016-05-08
  • 修回日期:  2016-06-05
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